The Upper Cretaceous Ostravice Sandstone in the Polish Sector of the Silesian Nappe, Outer Western Carpathians

GEOLOGICA CARPATHICA, APRIL 2016, 67, 2, 147—164 doi: 10.1515/geoca-2016-0010 The Upper Cretaceous Ostravice Sandstone in the Polish sector of the Silesian Nappe, Outer Western Carpathians

MAREK CIESZKOWSKI1, ANNA WAŚKOWSKA2, JUSTYNA KOWAL-KASPRZYK1 , JAN GOLONKA2, TADEUSZ SŁOMKA2, ANDRZEJ ŚLĄCZKA1, PATRYCJA WÓJCIK-TABOL1 and RAFAŁ CHODYŃ1

1Jagiellonian University, Institute of Geological Sciences, Oleandry 2a, 30-376 Kraków, Poland; [email protected], [email protected], [email protected], [email protected], [email protected] 2University of Science and Technology (AGH), Faculty of Geology, Geophysics and Environmental Protection, Al. Mickiewicza 30, 30-059 Kraków, Poland; [email protected], [email protected], [email protected]

(Manuscript received June 27, 2015; accepted in revised form December 8, 2015)

Abstract: The Ostravice Sandstone Member was identified and described as a lithostratigraphic unit in the Polish part of the Outer Carpathians. This division occurs in the lowermost part of the Godula Formation, is underlain by variegated deposits of the Mazák Formation or directly by the Barnasiówka and Lhoty formations, and overlain by the Czernichów Member of the Godula Formation. Domination by thick- and very thick-bedded sandstones, conglomeratic sandstones and conglomerates rich in calcareous clasts, mostly of the Štramberk-type limestones, is typical for the Ostravice Sandstone Member. These deposits are widespread between the Moravskoslezské Beskydy Mountains in the Czech Republic and the Ciężkowice Foothills in Poland. The documentation of the Ostravice Sandstone Member occurrence as well as the petrological, sedimentological features, and inventory of the carbonate clasts are presented here.

Key words: Outer Carpathians, Silesian Nappe, Late Cretaceous, Godula Formation, Ostravice Sandstone Member, lithostratigraphy, sedimentology, carbonate clasts.

Introduction 2012b and papers cited therein). Numerous papers were devoted to the litho- and biostratigraphy of Cretaceous and The Carpathians, one of the most important mountain ranges Palaeogene deposits of the sedimentary succession present in of the European Alpides, are divided into the Inner Car- the Silesian Nappe. Some of them proposed formalization of pathians and the Outer Carpathians domains (e.g. the Silesian Nappe’s deposits according to the Polish Strati- Książkiewicz 1962, 1965, 1972, 1977; Mahe 1974; Ciesz- graphic Code (Alexandrowicz et al. 1975; Racki & kowski et al. 1985; Ślączka & Kaminski 1998; Golonka et Narkiewicz 2006). A lithostratigraphy of the Upper Jurassic— al. 2005, 2006 and references therein). The Outer Car- Lower Cretaceous deposits of the Silesian Nappe in the pathians (with the exception of the Pieniny Klippen Belt) are Western part of the Outer Carpathians was proposed by also called the Flysch Carpathians because they are mainly a group of Polish and Czech geologists (Golonka et al. 2008). composed of the flysch facies (turbidites) and they consist of A proposal for the complete lithostratigraphy of the Upper a stack of nappes and thrust-sheets. The nappe succession in Jurassic—Lower Miocene deposits representing the Silesian the Polish sector of the Outer Carpathians from the highest to Nappe was prepared by Golonka et al. (2013a). These pro- the lowermost ones includes the Magura Nappe, Dukla posals were preceded by field research aimed at better identi- Nappe and Foremagura group of nappes, Silesian Nappe, fication and revision of the formalized lithostratigraphic Subsilesian Nappe, Skole Nappe, and Stebnik and Zgłobice units. The research enables the highlighting of some new units (e.g. Książkiewicz 1962, 1965, 1972, 1977; Bieda et al. facts, including the discovery that the Ostravice Sandstone 1963; Geroch et al. 1967; Koszarski et al. 1974; Cieszkows- described until now only from the Moravskoslezské Beskydy ki et al. 1985; Żytko et al. 1989; Lexa et al. 2000; Ciesz- Mts. in the Czech Republic also occurs in the Polish sector kowski 2003; Golonka et al 2005, 2006, 2013a; Ślączka et of the Outer Carpathians (Fig. 1) and forms the lowermost al. 2006; Golonka & Waśkowska-Oliwa 2007 and papers member of the Godula Formation (Late Cretaceous in age). cited therein). Sedimentation of these sandstones in the Silesian Basin The Silesian Nappe is one of the largest tectonic units of marks the initiation of a new Late Cretaceous—Early Palaeo- the Western Outer Carpathians (e.g. Roth & Matějka 1953; gene stage of development of the Outer Carpathian Andrusov 1959; Książkiewicz 1972, 1977; Eliáš 1979; domain (cf. Eliáš 2000; Picha et al 2006; Cieszkowski et al. Ślączka et al. 2006). It is composed of a continuous turbiditic 2009a). sequence up to six thousands metres thick or occasionally This paper concerns the Ostravice Sandstones. The authors more representing the Late Jurassic through to the Early paid attention to the development, lithostratigraphic posi- Miocene (e.g. Cieszkowski 1992; Ślączka & Kaminski 1998; tion, distribution and composition of these sandstones and Ślączka et al. 2006; Picha et al. 2006; Cieszkowski et al. their formal lithostratigraphy. www.geologicacarpathica.com 148 CIESZKOWSKI et al.

Fig. 1. Geological setting of the Ostravice Sandstone Member in the western sector of the Outer Carpathians (map after Lexa et al. 2000 — simplified).

Ostravice Sandstone Member Mazák Formation (Picha et al. 2006) (Fig. 2). Further to the east the thickness decreases to below 1000 m, and mostly Position of the Ostravice Sandstone Member within the ranges between 200 and 400 m. In the eastern part of the Godula Formation Polish Outer Carpathians this formation can be partly or completely replaced by variegated shales of the Mazák For- The Godula Formation is widespread in the Silesian mation (“Godula variegated shales”) as in the Bystre thrust Nappe in the western part of the West Outer Carpathians in sheet in the Bieszczady Mts. (cf. Ślączka 1959). The Godula Poland and the Czech Republic (e.g. Koszarski et al. 1959; Formation was described firstly in the Silesian part of the Koszarski & Ślączka 1973; Ślączka 1986; Słomka 1995; Carpathians as the Godula Beds, which were divided into Picha et al. 2006). It is composed of thick-, medium- and three parts: Lower, Middle, and Upper Godula Beds (e.g. thin-bedded glauconitic sandstones with intercalations of Książkiewicz 1933; Burtanówna et al. 1937; Geroch et al. grey shales. The presence of glauconite in sandstones is 1967; Unrug 1969; Burtan 1973; Koszarski & Ślączka 1973; a characteristic feature important for distinguishing the Godula Nowak 1973; Słomka 1995). In relation to this, Golonka et Formation. In the western part of the occurrence area, it al. (2013a) following partly Burtan (1973) and Wójcik et al. reaches the impressive thickness of up to 2500 m or even al- (1996) proposed formal lithostratigraphy for the sedimentary most 3000 m in the Moravskoslezské Beskydy Mts., 2000 m sequence of the Silesian Nappe and suggested dividing the in the Beskid Śląski (in Czech: Slezské Beskydy) Mts, and Godula Formation into a few lithostratigraphic members. about 1500 m in the Beskid Mały Mts. (Słomka 1995). The lower part of this formation should be divided into the North-east of the Beskid Mały Mts. the Godula Formation is Ostravice Sandstone Member which consists mainly of thinning and interfingering with variegated shales of the thick-bedded sandstones, and the Czernichów Member rep-

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resented by fine-grained, thin- and medium-bedded sandstones intercalated with black or grey shales. The middle part, developed as thick-bedded sandstones with thin shaly intercalations, is called the Skrzyczne Member. The upper part named the Wisła Member consists of thin- and thick- bedded sandstones and green shales. Conglomerates in the upper part, which were called the Malinowska Skała Con- glomerate Member (Burtan 1973), are widespread in the Beskid Śląski (Slezské Beskydy) Mts. and the Beskid Mały Mts. (e.g. Burtan 1973; Książkiewicz 1974; Słomka 1995). The age of the Godula Formation is estimated as the Turonian—Early Senonian time interval (Nowak 1973; Ciesz- kowski 1992; Słomka 1995; Ślączka & Kaminski 1998 and references therein), Turonian—Campanian/Maastrichtian boundary (Skupien & Mohamed 2008). The Godula Forma- tion is underlain by the variegated shales of the Mazák For- mation and overlain by the thick-bedded sandstones of the Istebna Formation. Taking into consideration the above-mentioned facts, we can state that the Ostravice Sandstone Member is the lowermost lithostratigraphic sub-division of the Godula Forma- tion. From the bottom it borders with the Mazák Formation. In many places the lower boundary of this member is erosive and the Ostravice Sandstone Member contacts directly with the Barnasiówka or even Lhoty formations. It is caused by the dynamic sedimentation of the sandy and conglomeratic deposits. From the top the Ostravice Sandstone Member borders the thin- and medium-bedded sandstone-shaly complex

Fig. 2. Lithostratigraphic log of the Late Jurassic—Cretaceous sedimentary succession of the Silesian Nappe exposing the position of the Ostravice Sandstone Member within the Godula Formation.

GEOLOGICA CARPATHICA, 2016, 67, 2, 147—164 150 CIESZKOWSKI et al. of the Czernichów Member. In the Moravskoslezské Besky- Thicker, amalgamated layers of up to 5 m also occur. The dy Mts. the transition between the Mazák Formation. and sandstone is medium- and coarse-grained, often conglome- Ostravice Sandstone Member of the Godula Formation can ratic (Figs. 3, 4, 5). Layers or lenses of fine conglomerate are be gradual and layers of sandstones rich in carbonate clasts not uncommon. Occasionally coarser conglomerate with could be interbedded with red shales (cf. Andrusov 1933). pebbles or clasts of exotic rocks (3—7 cm, occasionally even Anyway, the Ostravice Sandstone Member is widespread in up to 30 cm in size) occurs. In some layers limestone clasts the southern area of occurrence of the Godula Formation. of different sizes are so numerous that the rock takes on characteristics of sedimentary breccia. The thicker sandstone Name layers are usually massive, but in thinner layers parallel lamination occurs. In some cases dish structures can be noticed as The Ostravice Sandstone Member name was given after well as flame structures (Fig. 6). The sandstone is more or the Ostravice River in the Moravskoslezské Beskydy Mts., less rich in glauconite, which causes its grey-greenish Frýdek-Místek District, Ostrava Province, Morava Land, colour. In some parts of sections the thick-bedded sandstone Western Outer Carpathians, Czech Republic. deposits are intercalated with medium-bedded, medium- or Czech name: ostravický pískovec v godulských vrstvách. fine-grained glauconitic sandstones with more or less clearly Polish name: ogniwo piaskowca ostrawickiego (shortened developed sequences of Bouma intervals, very typical name: ogniwo ostrawickie). for the facial type of “Godula sandstone”. These are interbedded very rarely with grey-bluish marly or greenish clayey Area of occurrence shales. The sandstones and conglomerates are composed of mo- The Ostravice Sandstone Member is widespread in the nomineral grains as well as fragments of rocks. Bioclasts Outer Carpathians in the Silesian Nappe on the territory of such as fragments of corals, echinoids, crinoids, fragments the Czech Republic and Poland over a distance of about of crushed mollusk shells, and calcareous algae are also ob- 300 km, from the surroundings of Ostravice village to the servable (Figs. 7.1, 7.2). Detritic material is matted with car- surroundings of Gromnik village. Its outcrops were noticed bonate or carbonate-ferruginous cement. in the Moravskoslezské Beskydy Mts., Beskid Śląski The grains and pebbles are usually sub-rounded, but some (Slezské Beskydy) Mts., Beskid Mały Mts., and Wieliczka, of them are more or less angular, especially clasts of lime- Wiśnicz, Rożnów, and Ciężkowice foothills (Fig. 1). stones, which indicates their short transport to the point from which they flowed in turbidity currents to the deep sedimen- Type section tary basin. Some fragments of limestones reveal traces of synsedimentary erosion and redeposition, and they are allo- The abandoned quarry called “Mazák Quarry” located in dapic limestones consisting of limestone clasts inherent in the Ostravice river valley, on the right bank of the river, near detrital, medium- or coarse-grained carbonate matrix of the the tributary of Mazák Creek in Ostravice village (GPS coor- same age as clasts. dinates: 49°3225.9” N, 18°2624.8” E), Frýdek-Místek Dis- In general composition, the sandstones described above trict, Moravskoslezské Beskydy Mts., Czech Outer are similar to these common within the whole section of the Carpathians, Morava Land, Czech Republic (Figs. 1, 3.1—3.5). Godula Formation. However, a fundamental feature that allows us to easily distinguish the Ostravice Sandstone Reference section (proposed by authors) Member is the presence of numerous clasts of limestone in coarse-grained and conglomeratic sandstone. These whitish Abandoned quarry in Ustroń-Poniwiec, town of Ustroń, clasts, of different dimensions, are explicitly visible against Akacjowa Str., northern slope of Czantoria Mt., Beskid the dark grey sandstone background (Figs. 3, 4). Śląski Mts., Cieszyn District, Upper Silesian Province, Po- The thick-bedded sandstones of the Ostravice Member land (Figs. 1, 4). contain large olistoliths of older turbiditic deposits known from the sedimentary succession of the Silesian Nappe. Thickness Their lateral size is from several metres up to 100 m or more, and thickness 3—10 m or even more. They are clearly visible The member’s thickness in the type section is about only in big outcrops. 60—120 m, but in the Moravskoslezské Beskydy Mts. even a 150—400 m complex of thick bedded sandstones located at History the base of the Godula Formation is included in this division (Menčík in: Roth et al. 1962). East of the Beskid Mały Mts. The Ostravice Sandstone (in Czech: ostravický pískovec) the thickness of the Ostravice Sandstone Member is chan- within the sedimentary succession of the Silesian Nappe was geable but in general it decreases. named and first described by Andrusov (1933) from Moravia – eastern part of the Czech Republic. Its name is connected Dominant lithology with the name of the Ostravice River (Roth & Andrusov in: Andrusov & Samuel 1985, page 111) which has source in The Ostravice Sandstone Member is characterized by the the Moravskoslezské Beskydy Mts. and flows through the dominant occurrence of 0.7—2.0 m thick sandstone layers. nearby city of Ostrava. However, Andrusov (1933) did not

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Fig. 3. Exposures of the Ostravice Sandstone Member and Mazák Formation in the Mazák Quarry, Moravskoslezské Beskydy Mts., Czech Republic (3.1—3.5). Outcrop in Porąbka, Beskid Mały Mts., Poland (3.6) and the sample of the conglomerate from this locality (3.7).

GEOLOGICA CARPATHICA, 2016, 67, 2, 147—164 152 CIESZKOWSKI et al. explicitly write whether he named the sandstones after the recently called the Mazák Formation (e.g. Picha et al. 2006; Ostravice River or Ostravice village. However, it is apparent Golonka et al. 2013a). In Andrusov’s (1933) description on from the text that the second option is correct (cf. “...I call it page 196 we can find that the Ostravice Sandstone is de- Ostravice Sandstone because it has great extent near Ostra- veloped as thick-bedded, 2—4 m thick, light grey or light vice...”). The described sandstone is exposed there in the greenish, fine- to coarse-grained, silicified glauconitic sand- quarry located in the Ostravice river valley near the tributary stone layers. Between these layers thin intercalations of of Mazák Creek in Ostravice village. In the quarry the strongly glauconitic muddy-sandstones and red clayey Ostravice Sandstone overlaid the Godula Variegated Shales, shales appear. Conglomeratic intercalations with frequent

Fig. 4. Exposures of the Ostravice Sandstone Member in the Ustroń-Poniwiec Quarry as the proposed neostratotype. 1—2 – thick-bedded Ostravice Sandstone Member. 3—4 – whitish clasts of limestones explicitly visible against of the dark grey background. 5 – pebble of limestone in conglomerate.

GEOLOGICA CARPATHICA, 2016, 67, 2, 147—164 U. CRETACEOUS OSTRAVICE SDST IN SILESIAN NAPPE, OUTER W. CARPATHIANS 153 pebbles of quartz and significant clasts of the Štramberk Picha et al. (2006) (page 111) mentioned that thick, coarse Limestone occur in the sandstones. turbiditic sandstones and conglomerates representing the This characterization has been completed and partly ex- Ostravice Sandstone (sensu Andrusov 1933) interbed varie- tended. Matějka & Roth (1949) noted that the Ostravice gated pelagic and hemipelagic shaly deposits of the Mazák Sandstone in the Ostravice river valley occurs within the Formation (sensu Roth 1980). They noticed that the Mazák Godula Variegated Shales (Beds) and is represented mainly Formation was assigned by Hanzlíková (1973) to the by thick-bedded sandstone, discontinuous in many places. Cenomanian age. Their figs. 17A and 17B present the Menčík (in: Roth et al. 1962) included to this division stratigraphy and lithostratigraphic logs of Outer Carpathian a 150—400 m thick thick-bedded sandstone package occurring units in the Czech Republic. The Ostravice Sandstone is at the base of the Godula Beds in the S and SE surroundings marked there as an intercalation within the Mazák Formation. of Třinec which laterally replaced the shaly Variegated The deposits of the Ostravice Sandstone Member were not Godula Beds. Eliáš (1995, 2000) also described the Ostravice mentioned in the Polish literature almost to this time, with Sandstone from the Outer Carpathians in Moravia and noted the exception of a cursory consideration by Słomka (1995) that they formed a prograding sedimentary fan beginning the who conducted extensive and detailed research into the de- new Late Cretaceous evolutionary stage of the Silesian Basin. velopment and sedimentological features of the Godula For- Roth & Andrusov (in: Andrusov & Samuel 1985) stated mation in Poland and the Czech Republic. He studied the that the Ostravice Sandstone developed within the sedimen- Ostravice Sandstone in its stratotype area in the Moravsko- tary succession of the Silesian Nappe and forms a lithostrati- slezské Beskydy Mts., and noticed the origin of a submarine graphic division dominated by sandstones. In many places it fan formed by these sandstones at the foot of the north- overlays the Variegated Godula Beds, but also replaces them western slope of the Silesian Ridge in the Late Cenomanian. partly or completely. They described distinctive coarse and The occurrence, lithology, some sedimentological features, conglomeratic or even brecciated sandstones rich in lime- and lithostratigraphic position of the Ostravice Sandstone in stone clasts as well as light glauconitic noncalcareous sand- the Polish sector of Silesian Nappe between Ustroń and stones. The age of the sandstone was estimated as Tuchów area were briefly described by Cieszkowski et al. Cenomanian—Lower Turonian. (2010). Next, the micropalaeontological data from limestone Some specimens of macrofossils were found in some clasts from the Ostravice Sandstone in Poland were presented clasts of sediments redeposited into the Ostravice Sandstone. (Cieszkowski et al. 2011; Kowal et al. 2011). These sand- The ammonite Perisphinctes sp. and remnants of corals stones were also mentioned in some publications considering (Andrusov 1933) were noticed in clasts of the Štramberk- the existence and origin of olistostromes and olistoliths in type limestones, while in clasts of the Tešin-Hradište Beds the Outer Carpathians (e.g. Cieszkowski et al. 2009a, (recently called Cisownica Member of the Hradište Forma- 2012a, b). In a paper presenting the geology of the western tion) Early Cretaceous ammonite fauna was identified part of Polish Outer Carpathians, Golonka et al. (2013a) pro- (Foldyna & Šuf 1964). posed to recognize the Ostravice Sandstone as the lowermost member of the Godula Formation. Though the name “Ostravice Sandstone” was not used in Polish geological publications, some geologists noticed that in the thick- bedded sandstone at the base of the Godula Formation in the Be- skid Śląski Mts. (e.g. Ślączka and Kaminski 1998; Cieszkowski 2004; Cieszkowski et al. 2009b) or in the Beskid Mały Mts. (Książkiewicz 1951) clasts of limestones are abundant. Nowak (1957) in the Beskid Mały Mts. (river basin of Wielka Puszcza) from the lower part of the Godula Beds described conglomerates and sandstones composed mostly of quartz and clasts of the Cieszyn Limestone (which constitutes a distal, allodapic equivalent of the Štramberk-type limestones). One of the best outcrops of the Ostravice Sandstone Member lo- Fig. 5. The thick-bedded deposits of the Ostravice Sandstone Member in the Poniwiec Quarry cated in an abandoned quarry in (drawing by Marek Cieszkowski). Ustroń-Poniwiec was described in

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Fig. 6. Type I channel sequences in deposits of the Ostravice Sandstone Member in the Ustroń-Poniwiec Quarry section in the Beskid Śląski Mts. (after Słomka 1995, slightly modified). 1 – grain size: m — mud, s — silt, fs — fine sand, c- coarse sand, g- gravel. Lithology: 2 – shale; 3 – pebbly mudstone; 4 – micritic limestone; 5 – sandstone; 6 – conglomeratic sandstone; 7 – sandy conglomerates; 8 – conglomerates; 9 – thin, ripple-laminated sandstone beds (below 3 cm); 10 – thin, laminated and massive sandstone beds (below 3 cm); 11 – parallel lamination; 12a – wavy lamination; 13 – through cross stratification; 14 – dish structures; 15 – graded bedding; 16 – shale and/or limestone clasts; 17 – flat, even sole; 18– erosional and /or loaded sole. Cycles: 19 – positive cycle; 20 – negative (compensation) cycle; 21 – palaeocurrents directions. some geological guidebooks. Ślączka and Kaminski (1998) tinctive components of these sandstones. Cieszkowski described the Lower Senonian (Turonian—Lower Campa- (2004) also emphasized these features of deposits visible in nian) very thick-bedded sandstones of the lowermost part of the Poniwiec Quarry. The sedimentological features of the the Godula Beds outcropping there. They pointed out that Godula Formation were studied there by Słomka (1995). He the large olistoliths of turbiditic deposits were derived from presented lithological and sedimentological logs of the God- the Lower Cretaceous Lhoty Beds within the Godula sand- ula Beds that cropped out in the quarry, and noticed the oc- stones and noticed that clasts of limestones belong to the dis- currence of limestone clasts in sandy conglomerates.

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Fig. 7. Micrographs of calcareous clasts and bioclasts in sandstones and conglomerates of the Ostravice Sandstone Member: 1 – Echinoid spin; sample 18. 2 – Red algae Corallinaceae (arrows); sample UP3/3. 3 – Peloidal-bioclastic grainstone; sample OI/1. 4 – Limestone with peloids, Dasycladales algae fragments (D) and crinoid plate (C); sample OI/6. 5 – Oncoid wackstone; sample O/Po1. 6 – Ooid packstone; sample OII/1. 7 – Numerous poorly rounded limestone clasts (dark clasts); sample OIII/1. 8 – Fragment of limestone with coral; sample OII/2.

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Cieszkowski at al. (2010) stated that Ostravice Sandstone up to 50 cm across) sandstones with graded bedding, fol- occurs in the Ustroń-Poniwiec Quarry, but a more complete lowed upward by laminated sandstones and less common description of it was presented by Golonka et al. (2013b), diagonally bedded sandstones. Shale interbeds host lensoidal who also stated that this quarry can be a good reference sec- bodies of very fine-grained sandstones with ripplemarks. tion for the Ostravice Sandstone Member. Up the sequence, the amount of shales increases. Both successions described above represent the bottom Sedimentation, sedimentological features portion of the Godula Formation in the Beskid Śląski Mts. These are typical channel sequences of the internal fan Deposits of the Ostravice Sandstone Member from the (Słomka 1995) developed as: thick and very thick layers of Poniwiec Quarry in Ustroń are dominated by conglomeratic conglomeratic sandstones (SC facies), and massive sand- sandstone facies (SC) (Słomka 1995) in which the most stones (MS facies) accompanied by sandy conglomerates common variety is medium-grained sandstone with up to (CS facies) and sandstones with mudstones (SM facies, 30 vol. % of pebble fraction (Fig. 6). The average size of known only from the top part of the sequence). The upward- pebbles does not exceed 3 cm although boulders (up to decreasing thickness of layers and grain size of sediments 30 cm across) were also encountered. Deposits of this mem- is clearly visible (Shanmugam & Moiola 1988; Słomka ber form very thick layers (locally over 5 m) with numerous 1995). distinct amalgamation surfaces. The bottoms of the layers are erosional or deformational whereas the tops are flat or Petrology wavy. The pebble fraction always accumulates close to the bottoms of the layers. Up the sequence, pebbles can form Thin-section investigations from samples taken from de- thin lenses or streaks (sSC subfacies – bedded conglomeratic posits of the Ostravice Sandstone Member reveal composi- sandstones) or are randomly scattered within the framework tion and sedimentary microstructures. Detrital material is (mSC subfacies – massive conglomeratic sandstones). texturally immature. The sizes of grains vary over a wide The roundness of pebbles is variable but sub-rounded grains extent from 0.2 to 20 mm (extremely up to 10 cm). The ma- predominate. In some layers, perfect examples of blow-type jority of large clasts of the gravel fraction are poorly to well- and droplet-type structures can be encountered. The con- rounded, whereas the background (grain size 0.5 mm in glomeratic sandstones facies is accompanied by sandstone ave-rage) consists of angular grains. The sandy fraction facies (S), which shows very thick or thick layers with flat framework consists of: quartz occurring as singular grains bottom surfaces. Blurred load casts are also present. The and polycrystalline aggregates; feldspar, mainly altered sandstone facies (S) includes two subfacies: massive sand- orthoclase, rarer plagioclase; mica (mainly muscovite plus stones (mS) and massive sandstones with bowl-types struc- minor amounts of biotite); glauconite; heavy minerals tures (mqS). Medium-bedded sandy conglomerates facies (abraded grains and euhedral crystals of rutile, tourmaline, (CS) and sandstones with mudstones facies (SM) are rather zircon) (Fig. 9). scarce (Słomka 1995). Gravel-sized grains appear separately, dispersed by finer In the bottom part of the Ostravice Sandstone Member material. There are quartz mono- and polycrystalline and succession an olistolith can be observed as a few-metres- pieces of rocks (intrusive and extrusive igneous rocks, meta- thick sliding wedge of mudstones with sandstones (MS fa- morphic schists and gneisses as well as sedimentary rocks, cies) of the Lhoty Formation jammed within the Ostravice e.g. sandstones, mudstones, cherts, limestones, and coal). Sandstone Member (cf. Słomka 1995). Matrix occurs in minor amounts within interstitial spaces The mining operations carried on in the Obłaziec Quarry between the framework grains. Occasionally it is ferric. exposed a diverse succession of the Godula Formation Detritus is cemented by crystalline calcite, which corrodes (Fig. 8). In its bottom part several-metres-thick SM facies grain surfaces. (sandstones with mudstones) can be observed. These are Granites are phaneritic, medium-grained rocks consisting fine-, rarely medium-grained sandstones with graded bed- of ca. 70 % alkali feldspar, 25 % quartz, and minor amounts ding and parallel lamination. Sandstone beds show flat bot- of biotite. The feldspar grains tend to be between 0.5—1 mm tom and top surfaces. Thin interbeds of mudstones, thin to in size on average. They occur generally as colourless anhe- medium beds of micritic limestones with locally developed, dral grains. Dusty alteration is visible. Orthoclases damaged poorly visible parallel laminations as well as very thin len- by speckled sericite replacement represent the majority of soidal intercalations of cross-laminated sandstones are com- feldspars. Only minor amounts of albite have been observed mon. Up the sequence, we observe very thick- to thick- as discrete twinned grains. The quartz is clear and unaltered bedded conglomeratic sandstones with a total thickness of with sweeping extinction under crossed nicols. The quartz nearly 40 metres. The qSC subfacies (conglomeratic sand- grains tend to be between 1—3 mm in size on average, though stones with graded bedding) predominates (Słomka 1995), smaller grains are common, often aggregated. The quartz accompanied by the less frequent gLSC subfacies (conglo- grains have anhedral habit. There are intergrowths with the meratic sandstones with graded bedding transitional to lami- orthoclase grains. The biotite is brown with single cleavage. nated sandstones) and by thick-bedded, medium-grained, It shows subhedral flaky habit. Numerous dark spots in massive sandstones. The conglomeratic sandstones grade biotite, called pleochroic haloes, are developed around small upward into a 4-metres-thick layer of SM facies (sandstones zircon inclusions. Chlorite represents a common product of with mudstones). These are medium- to thick-grained (pebbles biotite alteration.

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Strongly altered basalt reveals an amygdaloidal structure phyroblasts of plagioclase are enveloped by chlorite-sericite (Fig. 9). The matrix originally composed of augite, plagio- or quartz-albite aggregate. Gneisses are medium-grained, clase, and olivine is entirely changed. Olivine is replaced by heteroblastic rocks, of intermediate texture between massive serpentine with admixture of iron ores and chalcedony, and schistose. Biotite, which does not form continuous layers, which in turn are replaced by carbonates. Vesicles are filled is corroded and intergrown with muscovite. Orthoclase occurs with chlorite, quartz, chalcedony and calcite. in somewhat larger grains. Quartz shows cataclasis. Another type of extrusive igneous rocks is characterized Sedimentary rock clasts are represented by the following by well-developed trachytic structure. Parallel lying feldspar lithotypes: fine-grained, quartzitic sandstones; dark, non- plates (1 mm length) are embodied in the feebly developed calcareous mudstones; clayey shales; cherts composed of matrix, consisting of the plagioclase mixed with quartz and chalcedony stuff with recrystallized, circular tests (radiolarian, pyroxene (often replaced by chlorite). Hematite occurs as sponge) therein; limestones. Sandstones and shales represent reddish pigment. recycled turbiditic deposits. The metamorphic rock assemblage contains quartzite, schists and gneisses (Fig. 9). Quartzitic rocks reveal grano- Carbonate clasts blastic or porphyroblastic structure. The parallel texture is due to more abundant biotite, dispersed in bands or lenticular Fragments of light coloured limestones constitute the most quartz aggregates enveloped by fine-grained quartz. Mica characteristic component of deposits of the Ostravice Sand- schists are a medium grained rock of homeoblastic and thin stone Member (Figs. 3, 4, 7). The carbonate clasts were studied schistose structure. The rock is composed of quartz, biotite, in detail in thin sections. The analysed clasts are poorly and rarer muscovite. Quartz is xenoblastic and usually flat- rounded and measure from less than 1 mm to several centi- tened. Micas are present in thin flakes and parallel aggre- metres, mostly 1—5 mm. gates, arranged separately or in layers often wavy deformed. It is possible to recognize such types of limestones as bio- Sericite-chlorite schists are fine-grained, phyllitic rocks. Por- clastic wackstone, oncoid wackstone, bioclastic-peloid wackstone and packstone, peloid packstone, peloid-bioclastic grainstone, ooid grainstone, ooid-bioclastic grainstone, li- thoclastic-bioclastic grainstone. Boundstone microfacies are difficult to state with regard to the small size of limestone fragments, but a lot of calcareous clasts that could constitute fragments of microbial deposits were observed. Fragments of calcareous sponges and corals are also found, which may indicate the presence of some reefs formed by these groups of organisms in the source area. These limestones represent diversified deposits of the inner carbonate platform, platform margin, slope of platform, and probably also deeper shelf. Identified fossils indicate the latest Jurassic—earliest Creta- ceous (mainly Tithonian-Berriasian) age of the limestones (Kowal et al. 2011). The most important for the age determi- nation are calpionellids, most of which are poorly preserved, but some can be precisely identified: Calpionella alpina Lorenz (Fig. 10.1), Calpionella elliptica Cadisch (Fig. 10.2), Crassicollaria parvula Remane (Fig. 10.3), Calpionellopsis oblonga (Cadisch) (Fig. 10.4), Tintinnopsella carpathica (Murgeanu et Filipescu) (Fig. 10.5). Foraminifera occurring in these clasts are mostly typical for the carbonate platform environments, and are known from the Štramberk-type limestones, as well as from the Cieszyn Limestone Formation (e.g. Olszewska 2005; Ivanova & Kołodziej 2010). Among them miliolids are the most common (e.g. Moesiloculina cf. histri (Neagu) (Fig. 10.6), Ophthalmidium sp., Rumanolocu- lina sp.), as well as foraminifera of the genus Andersenolina, especially Andersenolina alpina (Leupold) (Fig. 10.7), Andersenolina elongata (Leupold) (Fig. 10.8), Anderseno- lina delphinensis (Arnaud-Vanneau, Boisseau & Darsac) (Fig. 10.9). Other important foraminiferal taxons recognized in the thin sections are: Mohlerina basiliensis (Mohler) Fig. 8. Type I channel sequences in deposits of the Ostravice Sand- (Fig. 10.10), Protopeneroplis ultragranulata (Gorbatchik) stone Member in the Wisła-Obłaziec Quarry section in the Beskid (Fig. 10.11), Troglotella incrustans Wernli & Fookes Śląski Mts. (after Słomka 1995, slightly modified). Explanation like (Fig. 10.12), Haghimashella arcuata (Haeusler), Uvigeri- in Fig. 6. nammina uvigeriniformis (Seibold & Seibold) (Fig. 10.13),

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GEOLOGICA CARPATHICA, 2016, 67, 2, 147—164 U. CRETACEOUS OSTRAVICE SDST IN SILESIAN NAPPE, OUTER W. CARPATHIANS 159 and foraminifera of the genera Arenobulimina, Bullopora, the Carpathians is estimated to the Turonian—Campanian Dobrogelina, Gaudryina, Glomospira, Lenticulina, Melath- range (e.g. Geroch & Nowak 1984; Olszewska 1997 and refe- rokerion, Nautiloculina, Neotrocholina, Paleogaudryina, rences therein) and is recently observed even in the Cenoma- Reophax, Spirillina, Trocholina, Textularia. In some clasts nian. The lower boundary of the Ostravice Sandstone Member calcareous dinoflagellate cysts were noticed: Colomisphaera is synonymous with the age of the directly underlying the Bar- minutissima (Colom), Committosphaera ornata (Nowak) nasiówka Radiolarian Shale Formation. Bąk et al. (2001 and (Fig. 10.14), Cadosina fusca fusca Wanner (Fig. 10.15), references therein), according to the integrating radiolarian Crustocadosina semiradiata semiradiata (Wanner) and foraminiferal data, indicated the earliest Turonian age of (Fig. 10.16), Colomisphaera sp. In the thin sections, other the uppermost part of the Barnasiówka Formation. The microfossils typical for the Upper Jurassic and Lower Creta- radiolarian assemblages have been classified to the lower ceous deposits of carbonate platforms and slopes of plat- part of the Alievium superbum zone (biozone after forms also appear: Crescentiella morronensis (Crescenti) – O’Dogherty 1994), while in the foraminiferal assemblages a very common microfossil, recently interpreted as nubecu- the first appearance of Uvigerinammina jankoi Majzon was larid foraminifera incrusted by cyanobacteria (Senowbari- noticed (Bąk et al., 2001). Daryan et al. 2008); Globochaete alpina Lombard – The sedimentation of the deposits of the Ostravice Sand- planktonic green alga; problematic alga Thaumathoporella stone Member probably took place only in the Turonian. The parvovesiculifera (Raineri); polychaetes Terebella lapil- preliminary results from the poor foraminiferal assemblages loides Münster; microproblematica Koskinobulina socialis derived from the upper part of this member are not strati- Cherchi et Schroeder; “Bacinellid” fabric. Fragments of graphically diagnostic. The occurrence of single specimens macrofossils occur in many clasts, especially fragments of of Uvigerinammina jankoi Majzon is noticed here. On the calcareous green algae of the order Dasycladales, bryozoan basis of micropalaeontological analysis Słomka (1995) sug- colonies, brachiopods, bivalves, calcareous sponges, and gested the Turonian or possibly Turonian—Coniacian age for corals. Moreover spines of siliceous sponges, radiolarians, the overlying Middle Godula Beds. Thus, the superposition calcimicrobes, echinoderms elements, shells of gastropods, of the Lower Godula Beds, containing in their lower part the and ostracods were noticed. Ostravice Sandstone Member, indicates the Turonian age. The age, fossils, and microfacies of the studied limestone This aspect is now being studied in detail. clasts indicate that they correspond to the Upper Jurassic— Lower Cretaceous exotic limestones, mostly shallow-water, Studied locations platform deposits – so-called Štramberk-type limestones, which commonly occur in deposits of the Outer Carpathians Moravskoslezské Beskydy Mountains (see e.g. Książkiewicz 1951; Morycowa 1968; Cieszkowski In the Moravskoslezské Beskydy Mts. the Godula Forma- 1992; Kołodziej 2015) and are compared with the Štramberk tion reaches record thicknesses of up to 2500 m or even more Limestone from Moravia (Czech Republic) (e.g. Eliáš & than 3000 m (Eliáš 1979). It is underlain by the variegated Eliášová 1984). Clasts of mudstones, often with calpionel- shales of the Mazák Formation. The Ostravice Sandstone lids probably represent deeper facies of the latest Jurassic Member makes up the basal, several dozen metres thick part and earliest Cretaceous. of the Godula Formation. The sandstone layers are thick, usually 2—4 m, intercalated occasionally with thin- or medium- Age bedded glauconitic fine-grained sandstones and grey noncalcareous shales. Sandstones are coarse-grained or The Ostravice Sandstone Member occurs in the lowermost conglomeratic, rich in clasts of limestones, so that they partly part of the Godula Formation. The sedimentation of the represent a kind of sedimentary breccia. A representative Lower Godula Beds started from the Early Turonian (e.g. outcrop of the Mazák Formation and the Ostravice Sand- Nowak 1963; Bieda et al. 1963; Geroch et al. 1967; Koszarski stone Member is exposed in the Mazák Quarry in Ostravice & Ślączka 1973; Hanzlíková 1973; Menčík et al. 1983; village (Roth 1980). Pieces of magmatic rocks typical for the Słomka 1995; Olszewska 1997 and references therein), only teschenite association, black cherts, and clasts of shales tens its eastern part was connected with the early Senonian of centimetres in size typical for the Lower Cretaceous Hra- (Słomka 1995). The foraminiferal assemblages from the dište Formation, were found within the sandstones. These Ostravice Sandstone Member are usually very poor, but in clasts include the Early Cretaceous fauna (Foldyna & Šuf some samples they are stratigraphically diagnostic and indi- 1964) with Lamellaptychus didayi (Coquand), Salfeldiella cate the Turonian Uvigerinammina jankoi biozone (zone cf. guettardi (Raspail), aucellids shells, juvenile forms of after Geroch & Nowak 1984; Olszewska 1997). The occur- snails, as well as flora Zamites göpperti Schenk, Baiera cf.

rence of the index taxon Uvigerinammina jankoi Majzon in cretosa Schenk. Turbidites consisting of thin- and medium- X

Fig. 9. Microstructures of coarse-grained sandstones and conglomerates of the Ostravice Sandstone Member. 1—4 – Texturally immature conglomerate, clasts of gravel fraction are rounded, grains of psammite are angular. Matrix fills up interstitial spaces of the framework. 5—6 – Clast of altered mafic volcanic rock with amygdaloidal structure. 7 – Quartzitic arenite with corrosive carbonate cement. 8 – Clast of trachyte. 9 – Granite exotic. Images under crossed nicols, excluding 6 taken using parallel nicols, transmitted light. Abbreviations (after Whitney and Evans, 2010): Ab — albite, Bt — biotite, Cb — carbonate minerals, Chl — chlorite, Glt — glauconite, Kfs — K feldspar, Qz — quartz, Qz — fibrous quartz = chalcedony, Srp — serpentinite.

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Fig. 10. Micrographs of selected microfossils from clasts of the Upper Jurassic and Lower Cretaceous limestones: 1 – Calpionella alpina Lorenz; sample O/Po2. 2 – Calpionella elliptica Cadisch; sample OIV/1. 3 – Crassicollaria parvula Remane; sample OI/8. 4 – Calpio- nellopsis oblonga (Cadisch); sample OIV/1. 5 – Tintinnopsella carpathica (Murgeanu & Filipescu); sample OIV/1. 6 – Moesiloculina cf. histri (Neagu); sample OII/1. 7 – Andersenolina alpina (Leupold); sample OIV/1. 8 – Andersenolina elongata (Leupold); sample O/Br. 9 – Andersenolina delphinensis (Arnaud-Vanneau, Boisseau & Darsac); sample O/Br. 10 – Mohlerina basiliensis (Mohler); sample O/Br. 11 – Protopeneroplis ultragranulata (Gorbatchik); sample O/PoB. 12 – Troglotella incrustans Wernli & Fookes; sample O/Po1. 13 – Uvigerinammina uvigeriniformis (Seibold & Seibold); sample OV/1. 14 – Committosphaera ornata (Nowak); sample OI/5. 15 – Cadosina fusca fusca Wanner; sample O/Po2. 16 – Crustocadosina semiradiata semiradiata (Wanner); sample O/Po2. bedded glauconitic sandstones and grey shales typical for the The name “Mazák Formation” was taken from the Mazák Godula Formation occur above the Ostravice Sandstone Quarry but this quarry is also important as a part of the typical Member. In some publications (e.g. Roth 1980; Picha et al (stratotype) exposures of the Ostravice Sandstone Member. 2006) the Ostravice Sandstone was described as a member within the Mazák Formation, but others claim that this sand- Beskid Śląski (Slezské Beskydy) Mountains. stone is directly overlaid by shaly-sandstone turbidites typi- In the Beskid Śląski (Slezské Beskydy) Mts. the Godula cal for the Godula Formation. Formation reaches the thickness of up to 2500 m or more.

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Here the Godula beds were first described in details by Bur- consists of a several tens of metres thick complex of the Os- tanówna et al. (1937), and then divided into three parts: travice Sandstone Member Sandstones rich in carbonate Lower, Middle, and Upper Godula beds and included in the clasts. The biggest clasts reach up to 10 cm or even occa- Godula Formation created firstly in the Silesian part of the sionally 15 cm. Thin- or medium-bedded shaly-sandstone Carpathians as the Godula Beds (cf. Unrug 1969; Burtan turbidites are developed above the Ostravice Sandstone 1973; Nowak 1973). Golonka et al. (2013a) following Bur- Member. In the uppermost part of the section thick-bedded, tan (1973), Wójcik et al. (1996) and Cieszkowski et al. coarse-grained or conglomeratic sandstones that steeply pass (2010) proposed a new formal lithostratigraphy of the Godula into the thick-bedded sandstones of the Istebna Formation Formation with a few lithostratigraphic members (see arrive. The Godula Formation is underlain by red shales of above). In the Beskid Śląski (Slezské Beskydy) Mts. the Os- the Mazák Formation. Red or variegated shales form occa- travice Sandstone Member is exposed in the northern foot- sionally thin intercalations within the Godula Formation. hills of this mountain range in Nýdek, Ustroń, Brenna, and The sandstones of the discussed member were used in the the southern suburbs of Bielsko-Biala. It lies directly on the Middle Ages to build some Gothic buildings in Czchów top of the Lhoty Formation and is covered by the shaly-sand- town. It is possible to see them in the walls of the defensive stone Czernichów Member. The variegated shales of the tower, which is located on a small hill composed of the Os- Mazák Formation have not been noticed at its base there. travice Sandstone, and the walls of the Gothic church in the The Ostravice Sandstone Member is well outcropped in the town centre. Clasts of the Štramberk-type limestones from Ustroń-Poniwiec abandoned quarry and its surroundings a few millimetres up to 12 cm, as well as separate algal frag- (Figs 4, 5, 6). Now this position is proposed as a parastrato- ments, pieces of corrals or echinoids can be seen in the sand- type of the discussed member (Golonka et al. 2013a, b). In stones used in walls. Part of the market is also paved with that place coarse-grained and conglomeratic sandstones as slabs of these sandstones. It is interesting that the presence of well as conglomerates are rich in clasts of carbonate rocks deposits from the Ostravice Sandstone Member in Czchów dominated by the Štramberk-type limestones. Clast dimen- was first noticed in the walls, and following these findings, sions range from a few millimetres up to several centimetres, the authors (Waśkowska and Cieszkowski) started looking and the largest are more than 20 cm in size (Ślączka & Ka- for them in the field. minski 1998; Cieszkowski 2004; Cieszkowski at al. 2009a, b). Large olistoliths of the deposits represented by the Lhoty Ciężkowice Foothill and Verovice formations are exposed within the thick- and The easternmost locality of the Ostravice Sandstone Mem- very thick-bedded sandstones (Ślączka & Kaminski 1998; ber was noticed east of the Biała Dunajcowa River. The Cieszkowski 2004; Cieszkowski at al. 2009a,b; Golonka et sandstone crops out here in the core of the Rzepienniki Anti- al. 2013b). cline in the surroundings of Gromnik village and in the Brzanka-Liwocz Anicline in the surroundings of Ryglice vil- Beskid Mały Mountains lage. The cores of these anticlines are composed of deposits In the Beskid Mały Mts. the Godula Formation is up to of the Mazák and Godula formations and limbs of the Istebna, 1500 m thick (Słomka 1995) or more in the western part. Ciężkowice, Hieroglyphic, and Krosno formations. The The Ostravice Sandstone Member is found in the western Godula Formation is developed here as thin- and medium- part of this mountain ridge in the basal part of the Godula bedded glauconitic sandstones and grey shales passing up Formation. Sedimentation of the Godula Formation began the section to the medium- and thick-bedded sandstones and there with a complex of thick- and very thick-bedded sand- shales. At the top of the section, thick-bedded, coarse- stones. In some places they overlie variegated shales of the grained, and conglomeratic sandstones occur. They are Mazák Formation. In the eastern part of the Beskid Mały somewhat similar to the Istebna sandstone facies, but with Mts. the Ostravice Sandstone Member has not been found. noticeable amounts of glauconite. Thick-bedded, conglome- A thin level of variegated shales and a complex of calcitur- ratic sandstones of the Ostravice Sandstone Member rich in bidites, described by Książkiewicz (1951) as siliceous marls carbonate clasts occur at the base of this complex. The Godula Turonian—Coniacian in age, called the Kaczyna Marls occurs Formation is underlain by red shales of the Mazák Forma- there at the base of the Godula Formation (cf. Cieszkowski tion, but interbeddings of variegated shales also occur within et al. 2001, 2003; Uchman & Cieszkowski 2008). Thick- the middle part and top of the section. The thickness of the bedded sandstones without clasts of carbonates occur in the Godula Formation in the Rzepienniki Anticline is estimated lower part of the Godula Formation in the section at Rzyki as 200—250 m and in Brzanka—Liwocz up to 400 m. village overlying a shaly complex several tens of metres thick. Small outcrops of deposits typical for this member appear in the Puszcza Wielka stream at Porąbka village Discussion (Fig. 3.6). The Ostravice Sandstone has been known as a lithostrati- Rożnów Foothills graphic unit of the Silesian Nappe since 1933 (Andrusov In the Rożnów Foothills, the Ostravice Sandstone Member 1933), and later was commonly used by Czech geologists in was noticed in Czchów and its surroundings in the southern the area of the Moravskoslezské Beskydy Mts., the West Outer limb of the Czchów Anticline. The Godula Formation is up Carpathians in the Czech Republic (e.g. Matějka & Roth to 800 m or more thick there (Cieszkowski 1992). Its base 1949; Roth et al. 1962; Andrusov & Samuel 1985; Eliáš

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1995, 2000; Picha et al. 2006 and papers cited therein). The authors distinguish these deposits as a lithostrati- When describing this division, the author paid special atten- graphic member – the Ostravice Sandstone Member of the tion to its lithological development and clearly noticeable in- Godula Formation. This member is developed in the lower- dividuality among the other Upper Cretaceous deposits of most part of the Godula Formation. The bottom of the the Silesian Nappe. Then the Ostravice Sandstone was clas- Ostravice Member borders the variegated shales of the sified as a facies within the Mazák Formation (Roth 1980; Mazák Formation, and at the top it is overlain by the Menčík et al. 1983). Czernichów Member of the Godula Formation. The Ostravice Sandstone also occurs in the Polish sector The Ostravice Sandstone Member is developed as thick- of the Outer Carpathians and belongs to the same lithosome bedded sandstones and conglomerates. The sandstones are as that known from the Moravskoslezské Beskydy Mts. The composed of quartz, glauconite, feldspar, muscovite, as well lithostratigraphic position, age, lithology, mineral composi- as lithoclasts of magmatic, metamorphic and sedimentary tion, and sedimentological features of these deposits are the rocks. The presence of numerous carbonate clasts represented same in the Czech Republic and Poland. Their lithological mainly by the Uppermost Jurassic-Lowest Cretaceous features clearly distinguish this unit from the other sand- Štramberk-type limestones is a characteristic feature which stones of the Godula Formation. This observation was ini- clearly distinguishes this member. tially provided by Słomka (1995). Field investigations found In general, the age of the Ostravice Sandstone Member is that this lithotype is widespread in the Polish sector of the estimated as Turonian. Outer Carpathians ad its outcrops continue eastward from the The discussed member is widespread in the Moravsko- Beskid Śląski (Slezské Beskydy) Mts. through the Beskid slezské Beskydy Mts. in the West Outer Carpathians in the Mały Mts., Wieliczka and Rożnów Foothills, several kilo- Czech Republic and continues eastward through to the metres east of the Biała River. Therefore, this unit has re- Beskid Śląski (Slezské Beskydy) Mts. and Beskid Mały gional range. Thanks to its unique diagnostic lithological Mts., as well as the Wieliczka, Wiśnicz, Rożnów, features, the Ostravice Sandstone is easy to distinguish and Ciężkowice foothills in Poland. map out. These thick-bedded sandstone deposits represent a characteristic sandstone lithotype rich in carbonate rocks Acknowledgements: Thanks are addressed to Barbara clasts mainly of the Štramberk-type. They form the sand- Olszewska for helpful discussion about microfossils, as well stone complex in the lowermost part of the Godula Forma- as to reviewers — Jacek Rajchel, Miroslav Bubík and Petr tion with well-defined upper and lower limits. Clearly Skupien for constructive comments on the manuscript. This visible diagnostic features are well-marked in both the verti- research has been financially supported by Ministry of Science cal and lateral directions within the Ostravice Sandstone sup- and Higher Education/National Centre of Sciences grant porting the previous observations distinguishing it as no. NN307 249733, and AGH grant no. 11.11.140.173. a separate lithostratigraphic unit within the Godula Formation. Therefore, the present authors propose treating this lithological unit as a lithostratigraphic member within the Godula References Formation. The definition and description of the proposed member fit the rules described in the Stratigraphic Codes Alexandrowicz W., Birkenmajer K., Burchart J., Cieśliński S., (Alexandrowicz et al. 1975; Racki & Narkiewicz 2006). Dadlez R., Kutek J., Nowak W., Orłowski S., Szulczewski M. The structure of the Ostravice Sandstone Member litho- & Teller L. 1975: Principles of Polish stratigraphical classifi- some formed by its lithostratigraphic position, petrographic cation, terminology and nomenclature. Instr. i metody badań geol. 33, 1—63 (in Polish). composition, and sedimentological features is important for Andrusov D. 1933: Brief information on geology of Moravian-Silesian understanding the history of sedimentation within the Sile- Carpathians. Věst. Stát. Geol. Úst. ČSR 9, 194—199 (in Czech). sian Basin as well as for reconstruction of the Silesian Ridge, Andrusov D. 1959. Geology of Czechoslovakian Carpathians. II. which was destroyed during the orogenic process in the West Vyd. SAV, Bratislava, 1—375 (in Slovak with German and Rus- Outer Carpathians. The changes of sedimentary regime, sian summary). which contributed to the origin of the Ostravice Sandstone Andrusov D. & Samuel O. (Eds) 1985: Stratigraphic dictionary of Member and the entire Godula Formation, began a new stage the Western Carpathians. Part 2 L—Z. GÚDŠ, Bratislava, in the Cretaceous evolution of the Carpathian basins. The 1—359 (in Slovak). Bąk K., Bąk M. & Paul Z. 2001: Barnasiówka Radiolarian Shale geotectonic reorganization of the Outer Carpathian basins Formation – a new lithostratigraphic unit in the Upper Ceno- took place at the beginning of the Late Cretaceous. The Sile- manian—lowermost Turonian of the Polish Outer Carpathians sian Basin sensu stricto was separated during this reorgani- (Silesian Series). Ann. Soc. Geol. Pol. 71, 2, 75—103. zation from the widespread proto-Silesian Basin, which Bieda F., Geroch S., Koszarski L., Książkiewicz M. & Żytko K. existed at least from the Late Jurassic. 1963: Stratigraphie des Carpathes externes polonaises. Bull. Inst. Geol. 181, 5—174. Burtan J. 1973: Explanation to detailed geological map of Poland Conclusions 1:50,000. Wisła Sheet. PIG, Warszawa, 1—37. Burtanówna J., Konior K. & Książkiewicz M. 1937: Carte geologique des Karpates de Silesie. PAU, Wyd. Śląskie, The deposits described in the Czech Republic as the Os- Kraków, 1—104 (in Polish with French summary). travice Sandstone of the Silesian Nappe continue eastward to Cieszkowski M. 1992: Michalczowa zone: a new unit of Fore- the Polish sector of the Outer Carpathians. Magura zone, Outer Carpathians, South Poland. Kwart. AGH

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